Ch 4 - Wind

Introduction Introduction –The motion of air is important in many weather- producing processes. –Moving air carries heat, moisture, and pollutants from one location to another – at times in a gentle breeze, occasionally in a pure hurricane. –Air movements create favorable conditions for the formation and dissipation of clouds and precipitation: in some cases, those motions cause the visibility to decrease to zero; in others, they sweep the skies crystal clear (Lester, 2006).

Ch 4 - Wind Introduction Introduction –Winds move atmospheric mass and therefore affect changes in atmospheric pressures. –As you will see, these pressure changes modify the winds. –All of these factors create reasons for the changeable nature of not only the wind, but also weather (Lester, 2006).

Ch 4 - Wind Introduction Introduction –In flight, winds can have significant effects on navigation. –Chaotic air motions cause turbulence which is, at least, uncomfortable and, at worst, catastrophic. –Should atmospheric winds change suddenly over a short distance, flight may not be sustainable (Lester, 2006).

Ch 4 - Wind Introduction Introduction –Without question, as a pilot, you must understand air motions for efficient and safe flight. –In this chapter, we consider the causes and characteristics of horizontal motions of the atmosphere. –The chapter material provides you with a practical understanding of important relationships between the wind, atmospheric pressure, and the earth’s rotation (Lester, 2006).

Ch 4 - Wind Introduction Introduction –You will also gain some insight into the important influences of friction between the moving air and the earth’s surface. –When you complete the chapter, you will not only have an understanding of the fundamental causes of wind, but you will also know how wind is measured and you will be able to interpret general wind conditions from isobars and contours on weather charts (Lester, 2006).

Ch 4 - Wind Section A – Wind Terminology and Measurements Section A – Wind Terminology and Measurements –METAR Wind Information Section B – Causes of Wind Section B – Causes of Wind Section C – Pressure Gradient Force Section C – Pressure Gradient Force –Causes of Pressure Gradients Section D – Coriolis Force Section D – Coriolis Force Section E – Geostrophic Balance Section E – Geostrophic Balance –Estimating Winds from Isobars and Contours –D-Values Section F – Friction Section F – Friction

Ch 4 - Wind Section G – Other Effects Section G – Other Effects –Wind Production by Vertical Motions –Accelerated Airflow

Ch 4 - Wind Section A: Wind Terminology and Measurements Section A: Wind Terminology and Measurements –Wind – horizontal air motions –Wind velocity – a vector quantity –Vector – a vector quantity has a magnitude and a direction –Scalar – temperature and pressure are examples of scalar quantities which only have magnitude

Ch 4 - Wind –Wind speed – the magnitude of the wind velocity usually expressed in nautical miles per hour (knots), statute miles per hour (mph), kilometers per hour, or meters per second –Wind direction – the direction from which the wind is blowing, measured in degrees, or to eight or sixteen points of the compass, clockwise from true north (360 degrees)

Ch 4 - Wind METAR Wind Information METAR Wind Information –Sustained speed – reported wind speeds and directions are usually one or two-minute averages; this average wind speed is also referred to as the sustained speed –Peak wind – the maximum instantaneous wind speed greater than 25 knots since the last hourly observation

Ch 4 - Wind Section B: Causes of Wind – the most important forces that affect air motions are pressure gradient force, coriolis force and frictional force Section B: Causes of Wind – the most important forces that affect air motions are pressure gradient force, coriolis force and frictional force

Ch 4 - Wind Section C: Pressure Gradient Force – the difference in pressure between two points divided by the distance between the points Section C: Pressure Gradient Force – the difference in pressure between two points divided by the distance between the points the larger the pressure difference, the greater the acceleration through the opening the larger the pressure difference, the greater the acceleration through the opening magnitude of the pressure gradient = (P1 – P2 / distance) magnitude of the pressure gradient = (P1 – P2 / distance) –Horizontal pressure gradient – the atmosphere causes air parcels to be accelerated across the surface of the earth toward low pressure when a horizontal pressure gradient force exists –Causes of Pressure Gradients Differential heating – creation of a horizontal temperature gradient by Differential heating – creation of a horizontal temperature gradient by

Ch 4 - Wind Thermal circulation – in general, the movement of air which results from differential heating Thermal circulation – in general, the movement of air which results from differential heating –thermal circulations have two horizontal branches an upper branch which is called the return flow and a lower branch; figure 4-6 sea breeze an upper branch which is called the return flow and a lower branch; figure 4-6 sea breeze

Ch 4 - Wind Section D: Coriolis Force – a deflective force resulting from earth’s rotation Section D: Coriolis Force – a deflective force resulting from earth’s rotation –it acts 90 degrees to the right of wind direction in the Northern Hemisphere and 90 degrees to the left of the wind in the Southern Hemisphere

Ch 4 - Wind Section E: Geostrophic Balance – Coriolis and pressure gradient forces tend to be equal in magnitude but opposite in direction Section E: Geostrophic Balance – Coriolis and pressure gradient forces tend to be equal in magnitude but opposite in direction –Geostrophic winds – the related wind is the geostrophic wind it is quite helpful in understanding the characteristics of wind and it provides a good approximation to the actual wind it is quite helpful in understanding the characteristics of wind and it provides a good approximation to the actual wind

Ch 4 - Wind ***When the isobars on the surface analysis chart are close together, the pressure gradient force is large and wind speeds are strong ***When the isobars on the surface analysis chart are close together, the pressure gradient force is large and wind speeds are strong

Ch 4 - Wind ***Wind directions can be inferred from isobaric patterns ***Wind directions can be inferred from isobaric patterns

Ch 4 - Wind ***Winds do not blow directly from large scale high pressure areas to low-pressure areas because of Coriolis force ***Winds do not blow directly from large scale high pressure areas to low-pressure areas because of Coriolis force

Ch 4 - Wind Estimating Winds from Isobars and Contours Estimating Winds from Isobars and Contours –***The 500 mb constant pressure chart is suitable for flight planning at FL 180 –observed temperature and wind information give approximate conditions along the proposed route

Ch 4 - Wind D-Values – the difference between the two (True Altitude (TA) – Pressure Altitude (PA)) D-Values – the difference between the two (True Altitude (TA) – Pressure Altitude (PA)) –the cross track geostrophic wind is proportional to the gradient in D-values along the flight track

Ch 4 - Wind Section F: Friction – the force that resists the relative motion of two bodies in contact Section F: Friction – the force that resists the relative motion of two bodies in contact –Skin friction – friction also occurs within fluids, such as the atmosphere and at the interface between fluids and solids –Form drag – caused by turbulence induced by the shape of the aircraft –Surface friction – describes the resistive force that arises from a combination of skin friction and turbulence near the earth’s surface –Boundary layer – a transition zone between large surface frictional effects near the ground and negligible effects above the boundary layer; figure 4- 12

Ch 4 - Wind ***Because of the decrease of surface frictional effects with height, the winds at 2,000 feet AGL tend to parallel the isobars ***Because of the decrease of surface frictional effects with height, the winds at 2,000 feet AGL tend to parallel the isobars –At the surface, winds cross the isobars at an angle toward lower pressure and are weaker than winds aloft

Ch 4 - Wind ***Wind is caused by pressure differences and modified by the earth’s rotation and surface friction ***Wind is caused by pressure differences and modified by the earth’s rotation and surface friction

Ch 4 - Wind Section G: Other Effects Section G: Other Effects –Wind Production by Vertical Motions – see Figure 4-13 –Accelerated Airflow Centrifugal force – when air moves along a curved path, even if it is traveling at a constant speed, it is subjected to an acceleration Centrifugal force – when air moves along a curved path, even if it is traveling at a constant speed, it is subjected to an acceleration –the direction of motion is constantly changing along the path –this is known as centripetal acceleration –it is due to an imbalance in forces  when discussing this effect, some find it more convenient to refer to a force that produces the centripetal acceleration – the centrifugal acceleration

Ch 4 - Wind Cyclostrophic balance – coriolis force, the pressure gradient and centrifugal forces may be in cyclostrophic balance and produce cyclostrophic winds Cyclostrophic balance – coriolis force, the pressure gradient and centrifugal forces may be in cyclostrophic balance and produce cyclostrophic winds –the most dramatic examples of these are dust devils and tornadoes; figure 4-14

Summary The basic properties of horizontal motions of the atmosphere have been examined in this chapter. The basic properties of horizontal motions of the atmosphere have been examined in this chapter. You should now understand that air responds to pressure gradients by being accelerated toward lower pressure. You should now understand that air responds to pressure gradients by being accelerated toward lower pressure. Furthermore, pressure gradients are caused by temperature gradients and the movement of atmospheric mass by the winds. Furthermore, pressure gradients are caused by temperature gradients and the movement of atmospheric mass by the winds. Once the air is in motion, Coriolis force becomes important, especially in large scale atmospheric circulations (Lester, 2006). Once the air is in motion, Coriolis force becomes important, especially in large scale atmospheric circulations (Lester, 2006).

Summary The wind that results when Coriolis force is exactly in balance with the pressure gradient force is the geostrophic wind. The wind that results when Coriolis force is exactly in balance with the pressure gradient force is the geostrophic wind. Because the near balance of these two forces is common, the geostrophic wind has proven to be a very useful estimate of actual wind in a variety of applications ranging from the interpretation of isobars and contours on weather charts, to navigation. (Lester, 2006). Because the near balance of these two forces is common, the geostrophic wind has proven to be a very useful estimate of actual wind in a variety of applications ranging from the interpretation of isobars and contours on weather charts, to navigation. (Lester, 2006).

Summary Friction modifies the geostrophic balance, especially in the atmospheric boundary layer where its effect is apparent in cross-isobar airflow, turbulence, and gusty winds. Friction modifies the geostrophic balance, especially in the atmospheric boundary layer where its effect is apparent in cross-isobar airflow, turbulence, and gusty winds. Your knowledge of the basic causes and characteristics of wind will be of great value as you examine vertical motions, clouds, and weather in the next two chapters and, subsequently, specific atmospheric circulations (Lester, 2006). Your knowledge of the basic causes and characteristics of wind will be of great value as you examine vertical motions, clouds, and weather in the next two chapters and, subsequently, specific atmospheric circulations (Lester, 2006).